DALY: GEOLOGY OF THE NORTHEAST COAST OF LABRADOR. 247 
it is true that the serrateness of the Torngats is real and extensively 
developed, it will be well to present the evidence now in hand, which 
shows that, above a certain relatively low line, the range was, during 
the last advance of the great ice-sheet, not covered by a glacial mantle 
differing in any important way from the snow-blanket which overlies the 
country during the present winters. 
It is important to note that the discussion of the question will refer 
simply to the last advance of the ice. Until it has been determined 
whether there was once an interglacial period in Labrador corresponding 
to that recorded in the United States and southern Canada, we cannot 
be sure that a glacial topography, developed during the first advance, 
was not destroyed during interglacial time and during the time occupied 
in the second advance. It seems probable that the interglacial interval 
was longer near the zone of great terminal moraines than in Canada. 
Still further north the ice may have lain on the country throughout the 
whole glacial epoch. On the other hand, the Torngats may hold 
exactly the same relation to the rest of the peninsula as that of the 
Lofoden Islands to the Scandinavian mainland. An Alpine relief char- 
acterizes the island group to-day, although the ice-cap of the first glacial 
advance ran over the group far out into the Atlantic. 
The first attempt to solve the problem was made on the slopes of Mt. 
Ford. Ascending the mountain on the west side, typical roches mouton- 
nées and undoubted erratics cease at the sixteen hundred-foot contour. 
Above this, to the summit, the slope is one continuous Felsenmeer. 
Although unremitting search was carried on during the ascent, not a 
single erratic piece of rock was discovered above the contour mentioned. 
The creeping, frost-driven and snow-driven, fragments of ferruginous 
gneisses, trap, vein quartz, and syenite were found to be universally 
sharp-cornered, never subangular, and always deeply weathered. The 
few ledges protruding through the Felsenmeer were likewise profoundly 
affected by frost and general weathering, and nowhere presented the 
familiar smooth surface of a glaciated nubble’ of rock. While these 
contrasts between the Felsenmeer fragments and decayed ledges above 
and the fresh subangular erratics and roches moutonnées less than five 
hundred feet below, were very marked, there yet remained the possibility 
that the Felsenmeer really covered well glaciated bed-rock over which 
the rock fragments have streamed in postglacial times. The rarity of 
the ledges between sixteen hundred feet and the summit was such as 
not to permit of a satisfactory conclusion based on the study of this one 
mouutain-slope. On the south side, where the descent of Mt. Ford was 
